Toward all-scale simulation of moist atmospheric flows with soundproof equations

1. Toward all-scale simulation of moist atmospheric flows with soundproof equations Wojciech W. Grabowski1, Marcin J. Kurowski2, Zbigniew P. Piotrowski2, and Piotr K. Smolarkiewicz1 1National Center for Atmospheric Research Boulder, USA 2Institute of Meteorology and Water Management Warsaw, Poland

2. Traditional small-scale Boussinesq models are based on either elastic or anelastic (sound-proof) frameworks: Lipps and Hemler JAS 1982 Klemp and Wilhelmson JAS 1978 Explicit integration: acustic modes eliminated in the anelastic system Split-explicit integration: acustic modes integrated with time sub-stepping

3. Moist thermodynamics involve two aspects: • formulation of saturation conditions; • this determines if phase transition is supposed to happen • formulation of the precipitation physics; • this determines development and fallout of precipitation

4. Moist thermodynamics involve two aspects: • formulation of saturation conditions; • this determines if phase transition is supposed to happen • formulation of the precipitation physics; • this determines development and fallout of precipitation does not matter what system of equations is considered…

5. Moist thermodynamics involve two aspects: • formulation of saturation conditions; • this determines if phase transition is supposed to happen • formulation of the precipitation physics; • this determines development and fallout of precipitation there are some issues that need to be resolved…

6. Traditional small-scale Boussinesq models are based on either elastic or anelastic (sound-proof) frameworks: ! Lipps and Hemler JAS 1982 Klemp and Wilhelmson JAS 1978 Explicit integration: acustic modes eliminated in the anelastic system Split-explicit integration: acustic modes integrated with time sub-stepping

7. The key point: one needs to know T and p!

8. The key point: one needs to know T and p! Since typically potential temperature Θ is predicted, one needs pressure for converting Θinto T in addition to using it in qvs(p,T)…

9. 15-20 for tropospheric temperature range ~ 0.3

10. 15-20 for tropospheric temperature range ~ 0.3

11. ?

12. Small-scale dynamics: LES/CRM simulation ~ 5 K ~ 100 Pa (1hPa; ~ρu2) ~0.01 ~0.001

13. Pressure perturbations are typically neglected in anelastic small-scale models. Environmental pressure profile is used to convert Θ into T (e.g., Lipps and Hemler 1982). “Since dynamics only care about pressure gradient, dynamic pressure is only known to a constant and thus should not be used in thermodynamics…” (T. Clark, personal communication)

14. However, such a statement cannot be universally valid. For instance, in a funnel cloud or a tornado, condensation happens because pressure is significantly lower than in the unperturbed environment… u = 100 m/s, ρu2 ~100 hPa

15. Synoptic-scale dynamics: weather simulation ~ 10 K ~ 10 hPa ~0.01 ~0.01

16. Hydrostatic pressure variations associated with mesoscale and larger-scale weather systems need to be included in moist thermodynamics when converting Θ into T…

17. Can one use pressure from the elliptic pressure solver in the sound-proof system in the same way as the pressure in the compressible system? If the answer is yes, then our problems are solved!

18. We compare numerical solutions of relatively simple dry dynamics problems from anelastic and compressible EULAG model versions. Anelastic EULAG: standard (including moist processes). Compressible EULAG: dry gas dynamics equations (Smolarkiewicz and Szmelter JCP 2009).

19. 2D RISING BUBBLE SIMULATIONS Neutrally stratified environment Θ = 300 K Spherical 250-m initial perturbation ΔΘ = 0.5 K and 5 K Domain: 2 x 2 km2, gridlength: 12.5 m Timestep: 1/0.01 s (anel/compr) for ΔΘ = 0.5 K 0.2/0.003 s (anel/compr) for ΔΘ = 5 K 0.04/0.003 s (anel/compr) for ΔΘ = 50 K 0.01/0.003 s (anel/compr) for ΔΘ = 500 K

20. ΔΘ = 0.5 K; t = 15 min

21. ΔΘ = 0.5 K

22. ΔΘ = 5 K; t = 5 min

23. ΔΘ = 5 K

28. 2D HYDROSTATIC GRAVITY WAVE Stably stratified environment with a typical tropospheric stability Bell-shaped mountain, 10 km half-width, 314 m height Impinging flow: 10 m/s, decreasing with height (reverses at 12 km) Domain: 240 x 20 km2, gridlength: 500/375 m Timestep: 10/0.1 s (anelastic/compressible)

29. Pressure perturbations at t = 4 hrs:

30. Anelastic pressure solutions agree relatively well with the pressure field from the compressible system. It thus follows that one can use the elliptic pressure solution in the moist thermodynamics!

31. SUMMARY All-scale sound-proof simulation of atmospheric moist dynamics requires incorporation of the pressure perturbations into moist thermodynamics. With a proper design of the pressure solver, elliptic pressure solution agrees well with the solution from the compressible system. The compressible system is inefficient, but it does provide benchmark solutions to which anelastic solutions can be compared. Development of moist solvers that use the anelastic pressure solution and moist compressible solvers will follow, with specific model tests as outlined above.